in-formation on the environments and age of the BIL drainage is studying the contemporary fau-nal assemblages. Although a glacial lake has been a harsh environment for living organisms and microfossils are rare, it most likely was not without life. Trace fossils have been reported from several Pleistocene glacial lake deposits, closest examples being from Finland (Gibbard, 1977), Sweden (Högbom, 1893, 1915; Anders-son, 1897) and Lithuania (Uchman et al., 2009).
Holocene trace fossils have been studied close to the area studied here, by Virtasalo et al. (2006, 2011) and by Uchman & Kumpulainen (2011).
In older studies, there are reports of chirono-mid trails from Sweden (Högbom, 1893; Ander-sson, 1897) and Finland (AnderAnder-sson, 1897), as
Fig. 3. Sedimentological reconstruction of depositional settings prior to and after the Bil/Y transition Upper picture:
study sites depicted before Bil drainage. lower picture: situation just after the drainage.
well as crustacean, annelid and possible fish trac-es from Sweden (Högbom, 1915). In addition, insect larval tracks from varved sediments relat-ed to the BIL/Yoldia Sea transition from Finland were described by Gibbard (1977). The trace fos-sil distribution in a Lithuanian Pleistocene pro-glacial lake indicated that food was distributed patchily and that summers and transitional peri-ods were the most active times of trace making and winters were less active or inactive (Uchman et al., 2009). In studies of Holocene trace fossil assemblages from the Archipelago Sea, Virtasalo et al. (2006) noted a succession in trace fossil assemblage. Glaciolacustrine rhythmites depos-ited ca 11 300 cal yr BP, characterized by low organic content, were found to be barren of trace fossils. During post-glacial lacustrine conditions, Palaeophycus and Arenicolites trace assemblag-es reflected domicile -based activitiassemblag-es. Later on increasing salinity, increasing sediment organic content and decreasing sea floor oxygen content
were seen as a Planolites-dominated assemblage.
Uchman & Kumpulainen (2011) studied Early Holocene proglacial lake sediments from Swe-den, which had deposited during the late Yoldia Sea phase or early Ancylus Lake phase, ca 11 000 cal yr BP. They interpreted traces as Mermia ichnofacies, and suggested that the ecosystem was strongly affected by the local sedimentation processes, arthropods and fishes living in the ba-sin, rather than glacially derived melt water and position of the glacier margin.
Uchman et al. (2009) suggested that a rel-atively uniform trace fossil assemblage, fit-ting generally to Mermia ichnofacies (Buatois
& Mángano, 1995), can be seen in Pleistocene glacial lakes in several regions. It is composed of arthropod trackways, grazing traces and fish traces. The level of oxygenation, availability of food or other factors controlled the change of ichnoassemblage rather than change in the wa-ter depth. The ecological development model for
two New England glacial lakes by Benner et al.
(2009) fits well in this idea. In the Benner et al.
(2009) succession, stage I represented a simple benthic system with pioneer invertebrates such as nematodes, oligochaetes, ostracods and chi-ronomids living on the lake bottom. These pio-neers could have been transmitted passively by insects and birds, or actively. The initial arrival of fish was seen in stage II. To survive, fish pio-neers would have needed an established benthos in the lake. The stage III trace fossils indicated crustacean and a more abundant fish population.
Stage IV represented an environment with a shift from a glacial water source to a non-glacial wa-ter-source with increasing velocity of undercur-rents. This meant less silt and clay in water and made it possible for fishes to breed.
It seems that there is potential to investigate trace fossils in varved sediments in southern Fin-land in order to gain more specific information on the facies change at the BIL/Yoldia Sea transi-tion. Furthermore, trace fossil assemblages could provide information on small-scale saline pulses, increase -decrease in the amount of suspended sediment and bottom oxia-anoxia.
6. conclusions
• The BIL drainage triggered topographically controlled debris flows in deep-water areas of the BSB. While drainage deposits occur more sporadically in the Gulf of Finland and northern Baltic proper, the drainage unit can be traced over long (~ 100 km) distances in the area close to the 1st Salpausselkä.
• The offshore drainage-related sediments were deposited in an environment unsuitable for OSL-dating, but they display a well-de-fined facies change both in relation to water-level fall and the arrival of saline water. The former can be used as a chronostratigraphi-cal horizon, since it was formed by a single,
well-dated event.
• Lag in the arrival of brackish water could be interpreted as an undefined time period be-cause of prevailing erosion or non-deposition in the basin after the drainage.
• The early Yoldia Sea phase is characterized in the foreshore and shoreface environment by shallow water formations and well-developed shore terraces. The first YI OSL-date (11 200 and 11 400 ±2700 yrs) was obtained from Renkomäki shore terrace, thus proving the potential of the method and the material for dating the BIL/Yoldia Sea transition.
• Statistical approaches, like the methods rou-tinely used in dendrochronology, combined with sedimentological observations were-proven to offer new possibilities in the con-struction and revision of varve chronologies.
• The BIL/Yoldia Sea transition represents a change in sedimentary environment which is potentially reflected in contemporary ich-nofacies assemblages, thus giving new per-spectives in studies of Late Weichselian pro-glacial environments.
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